Part 4 - Berg - Hughes Center

crevasse splay, and interdistributary bay facies were common, and in the upper Hosston a
marginal marine delta-fringe system existed.
The predominant arenaceous siliciclastics of the Hosston range from
claystones/shales, siltstones, very fine-grained sandstones to conglomerates resulting in
prolific hydrocarbon reservoirs that can be found from Texas, across Northern Louisiana
and into Mississippi (Beckman and Bloomer, 1953; Cullom et al., 1962; Gorrod, 1980;
Saucier et al., 1985; Garner et al., 1987). The thickness of the Hosston varies from a few
hundred ft to over 3,500 ft in Jackson Parish. Minor limestones and conglomerates, as
well as some lignites, are also present in the Hosston (Granata, 1963; Saucier et al. 1985).
In the Pine Island field, Caddo Parish, the non-marine beds of the Hosston are located
between 3,900 and 5,900 ft in depth. Hosston reservoirs can be reached at drilling depths
of less than 10,000 ft (3,000 m) over most of the productive trend in Texas and
Louisiana. The thickness of the Hosston ranges from a few hundred feet near the zone of
truncation in south Arkansas to over 3,500 ft in southern Jackson Parish, Louisiana
(Cullom et al., 1962). Accompanying the change in thickness there is also a change in
character of the formation from predominantly coarse red sandstones, often cherty,
interbedded with red shales in south Arkansas, to finer grained white sandstones and
siltstones interbedded with gray, green and red shales and oolitic limestones in the deeper
parts of the North Louisiana Salt Basin.
In Texas, the Travis Peak Formation (Hosston equivalent) was deposited as a
complex of fluvial and deltaic systems that rapidly prograded over a broad, shallow shelf
more than 100 miles (160 km) wide. Aggradation resulted in braided stream deposits that
were more than 2,000 ft (600 m) thick. The entire complex is considered a fluvial-deltaic
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